Payún Matrú

Coordinates: 36°25′19″S 69°14′28″W / 36.422°S 69.241°W / -36.422; -69.241
Source: Wikipedia, the free encyclopedia.

Payún Matrú
Payún Matrú seen from space, black tongue-like lava flows and orange volcanic cones next to a white caldera
Payún Matrú
Highest point
Elevation3,715 m (12,188 ft)[1]
Coordinates36°25′19″S 69°14′28″W / 36.422°S 69.241°W / -36.422; -69.241[1]
Geography
Payún Matrú is located in Argentina
Payún Matrú
Payún Matrú
Parent rangeAndes
Geology
Mountain typeShield volcano
Last eruption445 ± 50 years ago

Payún Matrú is a

Salado Basin volcanic fields, form the Payenia province. It has been proposed as a World Heritage Site
since 2011.

Payún Matrú developed on sediment and volcanic rocks ageing from the

lava flows. The Pleistocene Pampas Onduladas lava flow reaches a length of 167–181 km (104–112 mi) and is the world's longest Quaternary
lava flow.

Volcanic activity at Payún Matrú commenced during the Plio-Pleistocene period, and generated lava fields such as Pampas Onduladas, the Payún Matrú shield volcano and the Payun volcano. After the formation of the caldera, volcanism continued both within the caldera as lava domes and flows, and outside of it with the formation of scoria cones and lava flows east and especially west of Payún Matrú. Volcanic activity continued into the Holocene until about 515 years ago; oral tradition of local inhabitants contains references to earlier eruptions.

Name

In local dialect, the term Payún or Paium means "bearded", while the term Matru translates as "goat".[2] The field is sometimes also known as Payenia.[3]

Geography and geomorphology

Regional

Payún Matrú lies in the

geosites have been identified at Payún Matrú itself.[10]

The active field is part of the

Austral Volcanic Zone.[3] Other volcanoes in the region include the Laguna del Maule, almost due west from Payún Matrú.[12]

Local

Payún Matrú is a 15 km-wide (9.3 mi)

Wind erosion has created flutes, grooves and yardangs within the ignimbrites,[20] such as in the western sector where yardangs reach heights of 8 m (26 ft) and widths of 100 m (330 ft).[21] The total volume of this shield is about 240 km3 (58 cu mi).[22]

Labelled description of hills/mountains above a lake
View from within the caldera

A 7–8 km-long (4.3–5.0 mi)

trachyandesitic volcanism crop out there.[14] The caldera also contains a permanent lake known as "Laguna" that is fed by snowmelt and by occasional rainfall.[2]

Matrú's highest active point field is the

summit crater open to the north[17] and it has a volume of about 40 km3 (9.6 cu mi).[29]

  • A volcanic cinder cone, with a conical mountain rising in the background
    The Payun volcano
  • A conical mountain rising above yellow vegetation
    The Payun volcano
  • Black tongue-like lava flows spreading radially
    Payún Matrú seen from space

Payún Matrú volcanic field

Aside from the caldera, the field contains about 300 individual

strombolian cones.[17] These edifices are up to 225 m (738 ft) high[32] and are associated with lava flows[17] and pyroclastic units;[6] the vents in the Los Volcanes group are spread across two separate belts.[27] Wind-driven ash transport has formed ash tails at individual vents.[33]

Older lava flows have

aa lava with blocky surfaces.[34][32] Some flows have reached the Rio Grande River west of Payún Matrú, damming it; the river later cut through and formed table-like landforms and canyons.[35] One of these is a slot canyon[27] known as La Pasarela,[36] where the structures of lava flows such as joints in the rocks and vesicles are clearly visible.[6] The entire field covers an area of over 12,000 km2 (4,600 sq mi)[27] and some of its flows have reached the Llancanelo Lake north of Payún Matrú and the Salado River in the east.[37] The estimated volumes of the entire Payún Matrú volcano are as large as 350 km3 (84 cu mi); the volcanic edifice was generated mostly through Strombolian and Hawaiian eruptions.[38]

Several cinder cones, some forming an alignment
Cinder cones on the La Carbonilla fault

The cones are aligned along easterly or northeasterly lineaments[19] which correlate with geological structures in the basement,[39] and appear to reflect the tectonic stresses underground.[40] Among these lineaments is the La Carbonilla fracture which runs in east–west direction and crops out in the eastern part of the field; in the central sector it is hidden by the caldera and in the western it is buried by lava flows.[41] The La Carbonilla fracture is a fault[40] that appears to have been an important influence on the development of the Payún Matrú complex in general.[42] Fissural ridges and elongated chains of vents and cones highlight the control that lineaments exercise on the volcanic eruptions.[43] In the summit area, pumice cones are aligned along the caldera rim.[44]

Among the cones in Payún Matrú are the

recent age.[47] These cones are the source of conspicuous black lava flows in the western part of the field;[48] some lava flows are over 30 km (19 mi) long.[32]

Pampas Onduladas and other giant lava flows

Payún Matrú is the source of the longest

alluvial terrace of the Salado River[60] in the La Pampa Province.[37]

This compound lava flow moved over a gentle terrain

distal sector.[63] The unusually fast flowing lava[64] under the influence of its low viscosity and of a favourable topography[65] eventually accumulated to a volume of at least 7.2 km3 (1.7 cu mi), a surface area of about 739 km2 (285 sq mi) and depending on the measurement a length of 167–181 km (104–112 mi).[64] The process by which such long lava flows form has been explained as "inflation" whereby lava forms a crust that protects it from heat loss; the so protected lava flow eventually inflates from the entry of new magma, forming a system of overlapping and interconnected lava flow lobes. Such lava flows are known as "sheet flows".[58] Parts of the Pampas Onduladas lava flow have been buried by more recent lava flows.[25]

Together with the Þjórsá Lava in Iceland and the Toomba and Undara lava flows in Queensland, Australia, it is one of only a few Quaternary lava flows that reached a length of over 100 km (62 mi)[57] and it has been compared to some long lava flows on Mars.[66] Southwest from Pampas Onduladas lie the 181.2 kilometres (112.6 mi) long Los Carrizales lava flows, which have in part advanced to even larger distances than Pampas Onduladas but owing to a straighter course are considered to be shorter than the Pampas Onduladas lava flow,[67][68] and the La Carbonilla lava flow which like Los Carrizales propagated southeastward and is located just west from the latter.[51] Additional large lava flows are located in the western part of the field and resemble the Pampas Onduladas lava flow, such as the El Puente Formation close to the Rio Grande River of possibly recent age.[37] Long lava flows have also been produced by volcanic centres directly south of Payún Matrú,[69] including the 70–122 km (43–76 mi) long El Corcovo, Pampa de Luanco and Pampa de Ranquelcó flows.[70][71]

Hydrography and non-volcanic landscape

Apart from the lake in the caldera, the area of Payún Matrú is largely devoid of permanent water sources, with most water sites that draw in humans being either temporary so-called "toscales" or ephemeral.

closed basins[73] which are also found in the lavic area.[74]

Geology

West of South America, the

South America Plate[41] at a rate of 66–80 mm/a (2.6–3.1 in/year),[75] giving rise to the Andean volcanic belt. The volcanic belt is not continuous and is interrupted by gaps where the subduction is shallower[41] and the asthenosphere between the two plates missing.[76] North of the Payún Matrú, flat slab subduction takes place; in the past flat slab subduction occurred farther south as well and had noticeable influence on magma chemistry.[77] In general, the mode of subduction in the region over time has been variable.[11]

There is evidence of Precambrian[78] (older than 541 ± 0.1 million years ago[45]) and Permian-Triassic (298.9 ±0.15 to 201.3 ±0.2 million years ago[45]) volcanism (Choique Mahuida Formation)[79] in the region, but a long hiatus separates them from the recent volcanic activity which started in the Pliocene (5.333–2.58 million years ago[45]). At that time, the basaltic El Cenizo Formation and the andesitic Cerro El Zaino volcanics were emplaced.[80] This kind of calcalkaline volcanic activity is interpreted to be the consequence of flat slab subduction during the Miocene (23.03-5.333 million years ago[45]) and Pliocene,[13] and took place between twenty and five million years ago.[76] Later during the Pliocene and Quaternary the slab steepened, and probably as a consequence volcanism in the land above increased,[81] reaching a peak between eight and five million years ago.[15]

Local

The basement rock underneath Payún Matrú is formed by

Patagonian basalts.[37] The Andean orogeny during the Miocene has folded and deformed the basement, creating basins and uplifted basement blocks,[26] and the Malargüe fold and thrust belt underlies part of the volcanic field.[83] Oil has been drilled close to the volcanic field from sediments of Mesozoic age.[16]

Payún Matrú is part of the

Peru-Chile Trench.[11] The volcanic activity still relates to the subduction of the Nazca Plate beneath the South America Plate, however;[4] one proposed mechanism is that a Miocene change in the subduction regimen led to the development of extensional tectonics[77] and of faults that form the pathways for magma ascent,[17] while other mechanisms envisage changes in mantle characteristics.[84]

Payún Matrú is part of a group of volcanoes, with a string of volcanoes just to its south
Geological context of the volcanoes

Other volcanic fields in the region are the

monogenetic volcanoes.[85] The volcanic field is part of the larger Payunia volcanic province, which covers an area of about 36,000 km2 (14,000 sq mi)[86] in the Provinces of La Pampa, Mendoza and Neuquén[87] and is also known as the Payenia[77] or Andino-Cuyana volcanic province.[3] Monogenetic volcanism of mainly basaltic composition has been active here for millions of years accompanied by the formation of several polygenetic volcanoes[88][89] and volcanoes like Agua Poca,[90] generating more than eight hundred monogenetic cones[87] although historical eruptions have not been observed.[77] Further south are the Chachahuen and Auca Mahuida volcanoes,[3] while the Tromen volcano is located southwest from Payún Matrú.[91]

Lava and magma composition

The volcanic field has produced rocks with composition ranging from

clinopyroxene, olivine, plagioclase and sanidine, but not all phenocryst phases can be found in every rock formation.[93][94] Magma temperatures of 1,122–1,276 °C (2,052–2,329 °F) have been inferred.[95]

Volcanic rocks erupted at Payún Matrú resemble

Magnetotelluric[c] observations indicate the presence of a "plume"-like structure that rises from 200–400 km (120–250 mi) depth close to the edge of the Nazca Plate slab to underneath Payún Matrú; it may indicate that magma erupted in the volcanic field originates at such depths which would explain the ocean island basalt-like composition.[97]

The magma ejected at Payún Matrú originates during

crystal fractionation,[99] assimilation of crustal material[100] and magma mixing in magma chambers.[101] The magmas eventually reach the surface through deep faults.[38] The edifice of Payún Matrú acts as an obstacle to magmas ascending to the surface; this is why only evolved[d] magmas are erupted in the caldera area of Payún Matrú while basic magmas reached the surface mainly outside of the main edifice.[103]

archeological sites, although its use was not widespread in the region perhaps owing to its low quality, the difficulty of accessing the volcanic complex and that human activity in Payunia only began comparatively late in the Holocene and mostly from the margins of the region.[104] Further, Payun volcano is notable for large crystals of hematite pseudomorphs which originated in fumaroles.[105]

Climate, soils and vegetation

The climate at Payún Matrú is cold and dry

periglacial landforms have been observed.[110] Palynology data from south of the region indicate that the climate has been stable since the Late Pleistocene.[38]

The vegetation in the volcanic field is mostly characterized by sparse

xerophytic.[38] Soils are shallow and are mainly rocky to loess-like.[106] Representative plant genera are Opuntia cactus and Poa and Stipa grasses.[112] Payún Matrú is a refuge for a number of animals such as the armadillos, black-chested buzzard-eagle, condors, Darwin's rhea, guanaco, mara, Pampas fox or South American gray fox, puma and Southern viscacha.[107] Some lizards may have evolved on the volcanoes.[113]

Eruptions

The volcano is formed of many stratigraphic formations that were emplaced partly consecutively partly concurrently
Stratigraphy of Payún Matrú

The geological history of the Payún Matrú volcanic field is poorly dated

formations,[32] which are of Pleistocene to Pleistocene-Holocene age, respectively;[114] a Chapua Formation of Plio-Pleistocene age has been defined as well.[115] The eastern volcanism is also known as the Pre-caldera basaltic unit; a western counterpart to it is probably buried beneath younger eruption products.[23]

The first volcanic activity occurred west and east of Payún Matrú and involved the emission of olivine basalt lava flows.[40] The long Pampas Onduladas lava flow was erupted 373,000 ± 10,000 years ago[116] and buried parts of the 400,000 ± 100,000 years old Los Carrizales lava field;[37] both have hawaiitic composition.[117] The Payun volcano formed around 265,000 ± 5,000 years ago within a timespan of about 2,000–20,000 years.[35] Its inferred eruption rate of 0.004 km3/ka (0.00096 cu mi/ka) is similar to typical volcanic arc eruption rates such as at Mount St. Helens.[29]

The main Payún Matrú massif formed in about 600,000 years, with the oldest trachytic rocks dated to 700,000 years ago. It is comprised by the lavic and ignimbritic Pre-caldera Trachyte unit[23] and consists of trachyandesitic to trachytic rocks, with trachyte being the most important component.[13] The massif may have formed a tall edifice like the Payun volcano before caldera collapse.[68]

The formation of the caldera coincides with the eruption of the Portezuelo Ignimbrite[41]/Portezuelo Formation[17] and took place between 168,000 ± 4,000 and 82,000 ± 2,000 years ago.[e][34] This ignimbrite formation where it is not buried by younger eruption products[119] spreads radially around the caldera and reaches a maximum exposed thickness of 25 metres (82 ft);[24] it covers an area of about 2,200 km2 (850 sq mi) on the northern and southern sides of Payún Matrú,[17] and its volume is estimated to be about 25–33 km3 (6.0–7.9 cu mi).[119] The event was probably precipitated by the entry of mafic magma in the magma chamber and its incomplete mixing with pre-existent magma chamber melts,[95] or by tectonic processes;[103] the resulting Plinian eruption generated an eruption column, which collapsed, producing the ignimbrites.[17] Different layers of magma in the magma chamber were erupted during the course of the eruption[120] and eventually the summit of the volcano collapsed as well, forming the caldera; activity continued and emplaced lava domes[17] and lava flows in the caldera area. These post-caldera volcanic formations are subdivided into three separate lithofacies.[119]

Basaltic and trachyandesitic activity continued after the formation of the caldera.[1] Morphology indicates that the El Rengo and Los Volcanes volcanic cones appear to be of Holocene age, while the Guadaloso vents formed during the Plio-Pleistocene.[17] One age from the eastern side is 148,000 ± 9,000 years ago, it comes from northeast of the Payún Matrú caldera.[121]

Uneroded volcanic cones and dark basaltic lavas indicate that activity continued into the Holocene.

lava dams might form in rivers.[125] It is considered Argentina's 24th most dangerous volcano out of 38.[126]

Various dating methods have yielded various ages for late Pleistocene-Holocene volcanic eruptions:

  • 44,000 ± 2,000 years ago, surface exposure dating.[127]
  • 43,000–41,000 ± 3,000 years ago, surface exposure dating, El Puente Formation. Basaltic lava flows of this formation reach ages of about 320,000 ± 5,000 years, implying a prolonged history of emplacement.[128]
  • 41,000 ± 1,000 years ago, underlying the Los Morados lava flow.[129]
  • 37,000 ± 3,000 years ago, surface exposure dating,[127] close to the Rio Grande River.[51]
  • 37,000 ± 1,000 years ago, La Planchada fallout deposit.[130]
  • 37,000 ± 2,000 years ago, northwestern side of the caldera.[131]
  • 28,000 ± 5,000 years ago, potassium-argon dating, lava flow[130] on the westerly side.[132]
  • 26,000 ± 5,000 years ago, potassium-argon dating, close to the Rio Grande.[132]
  • 26,000 ± 2,000 years ago, potassium-argon dating, not the same as the 26,000 ± 5,000 flow.[132]
  • 26,000 ± 1,000 years ago, potassium-argon dating,
    rhyolitic lava flow in the La Calle group.[130]
  • 20,000 ± 7,000 years ago, north of the Payún Matrú caldera.[121]
  • 16,000 ± 1,000 years ago, underlying the Los Morados lava flow.[129]
  • 15,200 ± 900 years ago,[133] potassium-argon dating, lava flow on the northwesterly[130]-westerly side.[132]
  • 9,000 years ago, potassium-argon dating.[127]
  • 7,000 ± 1,000 years ago, potassium-argon dating, Escorial del Matru within the caldera.[130]
  • <7,000 years ago, potassium-argon dating, trachyandesitic lava flow[130] in the western part of the field.[132]
  • 6,900 ± 650 years before present, thermoluminescence dating on the Guadalosos cones[127] on an eastward running fracture.[118]
  • 4,670 ± 450 years
    before present, thermoluminescence dating.[127][118]
  • 3,700 ± 300 years before present, pumice fallout in and east of the caldera.[118]
  • 3,400 ± 300 years before present, trachytic lava flows.[118]
  • 2,000 ± 2,000 years ago, surface exposure dating, young looking lava flow in the west.[134]
  • 1,705 ± 170 years before present, trachytic volcanic bombs.[118]
  • 1,470 ± 120 years before present, thermoluminescence dating on Volcán Santa María[118] although a much older age of 496,000 ± 110,000 years ago has also been given.[55]
  • 515 ± 50 years[135] before present, thermoluminescence dating on Morado Sur cone[127] and on the Pampas Negras lapilli field.[118]
  • 445 ± 50 years before present, lava domes on the caldera margin.[118]

See also

Explanatory notes

  1. ^ A coulée is a particular type of lava dome which has flowed sideward like a lava flow.[18]
  2. Southern Volcanic Zone, separate from the main volcanic system in the Andes.[3]
  3. electrical conductivity underground.[96]
  4. ^ Evolved magmas are magmas which due to a settling of crystals have lost part of their magnesium oxide.[102]
  5. ^ A younger age of 4,860 ± 400 years ago has also been proposed.[118]

References

Citations

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General sources

External links

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